Depositional processes within the frontal icecored moraine system, Ragnar glacier, Svalbard.

DEPOSITIONAL PROCESSES WITHIN THE FRONTAL ICE-CORED

MORAINE SYSTEM, RAGNAR GLACIER, SVALBARD

M

E

, L

K

, I

S

, A

M. T

Manuscript received January 18, 2010 Revised version March 2, 2010

EWERTOWSKI M., KASPRZAK L., SZUMAN I. & TOMCZYK A.M., 2010: Depositional processes within the frontal

ice-cored moraine system, Ragnar glacier, Svalbard. Quaestiones Geographicae 29(1), Adam Mickiewicz University Press, Poznań 2010, pp. 27-36, Figs 4., Tabs 3. ISBN 978-83-232-2136. ISSN 0137-477X. DOI: 10.2478/v10117-010-0003-8

ABSTRACT. The marginal zone of the Ragnar glacier has been divided into four zones: ice surface, proglacial

lake, lateral moraine and frontal moraine complex. Detailed researches were carried out in the last one - frontal moraine complex consisting of three subzones: (1) outer moraine ridge, (2) culmination moraine ridge and (3) inner moraine plateau. The frontal moraine complex of the Ragnar glacier shows large variability of lithofacies and depositional processes. The aim of this study was to reconstruct the intensity and variability of depositional processes from early stage of the frontal ice-cored moraines creation till present situation. Debris fl ow proc-esses, glaciofl uvial and glaciolacustrine sedimentation as well as aeolian activity and down- and backwasting are identifi ed as most important processes. Intensity of these processes has varied through the time. Presently the frontal ice-cored moraine complex of the Ragnar glacier is relatively stable, except few areas affected by the river or streams.

KEYWORDS: ice-cored moraines, depositional processes, sedimentology, Spitsbergen, Arctic

Marek Ewertowski, Leszek Kasprzak, Izabela Szuman, Aleksandra M. Tomczyk, Adam Mickiewicz University, Institute of Geoecology and Geoinformation, Department of Geomorphology, Dzięgielowa 27, 61-680 Poznań, Poland, evert@amu.edu. pl, l.kasp@amu.edu.pl, szuman@amu.edu.pl, alto@amu.edu.pl

Introduction

Resedimentation processes are one of the most important mechanisms of transformation of glacial environment. Most glacial landforms and sediments are modifi ed to some extent by post-depositional activities. Knowledge of these processes is crucial in the interpretation of sedi-mentary record of past glaciations (Bennet et al., 2000). Therefore, study of contemporary glacial landsystems is vital for better understanding of Pleistocene features.

This study concentrates on the moraine com-plex of the mountain, Arctic glacier Raganr. Simi-lar moraine ridges have been described from gla-ciers on Svalbard (e.g. Klimaszewski, 1960; Boul-ton, 1967, 1972; Kłysz, 1985; Karczewski, 1989; Stankowski et al., 1989; Huddart & Hambrey, 1996; Bennet et al., 2000; Etzelmüller, 2000; Lyså & Lønne, 2001; Sletten et al., 2001; Lønne & Lyså, 2005; Lukas et al., 2005) as well as from other Arctic areas (e.g. Goldthwait, 1951; Östrem, 1959; Hooke, 1970, 1973; Szupryczyński & Kozarski, 1970; Evans, 1989; Kjær & Krüger, 2001).

Fig. 1. A - Location of the study area, based on map from Rachlewicz et al. (2007). B – Morphological zones of the Ragnar glacier

The aim of this study was to reconstruct the in-tensity and variability of depositional processes for high-Arctic Ragnar glacier. The depositional proc-esses were interpreted based on sediments obser-vation within the outcrops and on the surface.

Study Area

Study area is located near the Petuniabukta (Petunia Bay) in the northern part of the Bille-fjorden (central part of Spitsbergen) (Fig. 1A). The

Ragnar glacier is an outlet glacier fl owing from the Mittag-Leffl er glacier that drains the Lomono-sovfonna (Lomonosov ice fi eld). The glacier is 4.9 km long and covers 6.6 km2_{. The}

contempo-rary ice edge is situated c. 80 m a.s.l. and is 400 m wide. According to Rachlewicz et al. (2007), its area was reduced by 1.2 km2_{between the Little Ice}

Age (LIA) and 2002, and its ice surface was low-ered by 65 m between 1960 and 2002. The mean fl ow velocity reaches 3.8 – 11.1 m a-1 _(Rachlewicz,

2004). The marginal zone of the Ragnar glacier is about 1.5 km long and 1 km wide. It was divided into four zones (Fig. 1B) based on geomorpho-logical criteria: (1) frontal moraine complex, (2) lateral moraine complex, (3) proglacial lake and (4) ice surface. In this study we considered only the frontal moraine complex including: the outer and the culmination ridge and also the moraine plateau. Sandur plain was developed in the front of the moraine complex. The large Ragnar river (up to 25 m wide and 1 m deep) cuts the frontal moraine complex in the northern part.

Methods

The sedimentological analyses were done to-gether with a detailed GPS mapping of the ice-cored moraine complex during the summer sea-sons 2005 and 2007. The preliminary assessment was based on the geological and geomorphologi-cal map (1:40,000, Karczewski et al. 1990) as well as on satellite imagery and aerial photographs which were used to measure the dimension of the main landforms.

Several outcrops were dug to document de-posits (Fig. 4). Sedimentological descriptions were done based on lithofacies analysis. Litho-facies is the basic unit used to describe the sedi-ment, depicted by a stratum of defi ned fabric properties (Miall, 1977; Zieliński, 1993). Fabric can gives information about transport and depo-sition history of sediments. The lithofacies in this study are defi ned by code after Miall (1977, 1978) and Zieliński (1992, 1995). The upper case letter describes the textural property and lower case letter describes the structural property (Table 1). The glacial diamicton was described with lithofa-cies code as proposed by Krüger & Kjær (1999). Diamictons are marked by the D letter. The lower

TABLE 1. LITHOFACIES CODE SYMBOLS FOR SORTED SEDIMENTS

(BASEDON MIALL, 1977, 1978) AND ZIELIŃSKI, 1995)

Symbol Texture D diamicton B boulders G gravel GS gravel sandy SG sandy gravely S sand

SF sand, fi ne-grained admixture

F fi nes

Symbol Structure

m massive

h horizontal lamination, stratifi cation

w wavy lamination

rc ripple cross-lamination of climbing _type p planar cross-stratifi cation

t trough cross-stratifi cation

TABLE 2. LITHOFACIES CODESYMBOLSFORUNSORTEDSEDIMENTS

(BASEDON KRÜGER & KJÆR, 1999). Symbol

D diamicton

General apperance

m massive

s stratifi ed

Granulometric composition of matrix C _{sandy-gravelly}coarse grained

M medium-grained matrix,_silt-sandy F fi ne grained,_clayey-silty

Clast/matrix relationship

(c) clast supported

(m1) matrix supported, _{clast poor}

(m2) matrix supported,_{clast moderate}

case letter describes the structure of deposits. Next letters characterize the matrix type and matrix to clast relation (Table 2). Additionally, structure of the lithofacies and the contact (gradual, erosive or sharp) between the strata were described.

Deposits and processes within the

frontal ice-cored moraine complex

The frontal ice-cored moraine complex has been described below according to subzones (Fig. 2): (1) outer moraine ridge – subzone I, (2) culmination moraine ridge – subzone II, (3) inner moraine plateau – subzone III.

Subzone I –outer moraine ridge

Subzone I consists of series of small hillocks and depressions between them. Clast-supported massive diamicton – DmM(c) is the main litho-facies in the subzone I. Fine-grained material

occurs in the hollows – mainly the lithofacies of horizontally or wavy laminated sands and silts (Sh, SFh, Fh). Two inactive debris fl ows were ob-served in the subzone I.

Outcrop A - Debris fl ow deposits (Figs 3B and 3C)

Debris fl ow deposits are represented by massive diamicton with silty matrix – DmF(c). A big quantity of coarse clasts (clast-supported diamicton) and lack of segregation suggest that diamictons were deposited by mass-fl ow processes. Large amount of fi ne-grained matrix indicates that cohesion was main force of transport of clasts. This is the type I of fl ow deposits according to Lawson (1979).

Subzone II – culmination moraine ridge

Subzone II is the most distinct feature in the frontal moraine complex. The highest hills of the frontal complex occur in the distal part

Fig. 3. A – Deformed glaciolacustrine deposits; B – Debris fl ow deposits with small amount of clasts; C – Debris fl ow deposits with large amount of clasts and fi ne-grained matrix; D – Glaciofl uvial deposits; E – Debris fl ow deposits – clast-supported

(i.e. further from the lake) of this subzone. The hillocks in the inner part (i.e. closer to the lake) are lower. The series of small depressions and hollows are typical for this inner part as well. Some exposures of ice-cores are in the SE part. Hillocks on the culmination ridge are built mainly of lithofacies of massive, matrix-supported diamicton – DmM(m2). Fine grained lithofacies (Sh, SFh, Fh) occur in the hollows. Two exposures in subzone II show mainly debris-fl ow deposits and fi ne-grained lacustrine sediments.

Outcrop B – Debris fl ow deposits (Fig. 3 E)

The outcrop in the SE part of culmination ridge shows lithofacies of clast-supported, mas-sive diamicton with sandy to silt matrix - DmM(c). The deposits are compact. Diamicton was depo-sited by cohesive debris fl ow (fl ow type I – Law-son, 1979). Signifi cant thickness and poor sorting suggest short range transport and deposition due to “freezing” - which is confi rmed by irregular positioning of the clasts (Zieliński & van Loon, 1996).

Outcrop C - Glaciolacustrine sediments (fi g. 3 A)

The exposure is located in the middle part of the culmination ridge. Two lithofacies are iden-tifi ed: massive, matrix-supported - DmF(m1) and massive sandy diamicton (SDm), both with poor clasts content. In case of DmF(m1) ma-trix is fi ne grained, silty whereas mama-trix within SDm is mostly medium grained, sandy to silty. Soft sediments deformations visible in the out-crop represent folds and fl owage lobes. Both lithofacies (DmF(m1) and (SDm) are character-istic for glaciolacustrine sub-environment with changeable energy of sedimentation. Most like-ly, the diamictons were previously deposited in horizontal position, within the periodically existed pond. Sandy lithofacies were deposited during the periods of lower transported-energy of stream fl owing into the pond. In both cases (DmF(m1) and SDm) the role of water in trans-port was high, with water content over 25% (Boulton & Paul 1967). DmF(m1) lithofacies is much thinner than SDm and occurs in the bot-tom part. Such features indicate a debris fl ow-age in the early stow-age of pond fi lling. Later, the

streams energy was decreasing and sandy mate-rial was delivered. The fi ne matemate-rial (Fm in the top of the exposure) was deposited in one of the latest stages. Fm lithofacies refl ects the decanta-tion process and steady-state condidecanta-tion.

The sediments, previously deposited in the depression, presently occur in the top part of the hill. It means that at least one topography inver-sion took place.

Subzone III – moraine plateau

Subzone III consists of numerous water ponds and depressions separated by generally low hillocks, but few higher elevated hill also occur. The subzone III contains many fi ne grained sediments, as a result of glaciolacustrine sedimen-tation in the ponds. Low hillocks are covered by massive matrix supported diamicton, with low quantity of clasts – DmM(m1).

Outcrop D – glaciofl uvial deposits (Fig. 3D)

One exposure was dug in the northern part of the subzone, near the river bank. Seven lithofacies are recognized in the vertical profi le: Lithofacies represent three different groups of sediments: (1) Hyperconcentrated fl ow deposits - Gm, (2) low/ medium-energy glaciofl uvial deposits - FSh, SGh, Src, SFh and (3) high-energy glaciofl uvial sediments - GDp, GDm. Each of group refl ect se-parate processes and subenvironments.

Hyperconcentrated fl ow deposits

Massive gravel (Gm) with sandy matrix is recognized in the bottom part of the exposure. The contact between lithofacies Gm and over-lying lithofacies of horizontally laminated sands and silts (FSh) is depositional. Lack of sorting and lamination suggest that lithofacies Gm was deposited in the high-energy sub-environment, probably during hyperconcentrated fl ow.

Low/medium-energy glaciofl uvial channel

Two lithofacies of SFh and three of FSh 1.

are above the lithofacies Gm.

Lithofacies of sand with ripple-cross la-2.

mination Src occurs above the second lithofacies of SFh. The angle of ripples climb is c. 20o_.

. The

gradual but the contact between Src and higher lithofacies SGh is sharp (erosive).

The lithofacies of horizontally stratifi ed 3.

gravelly sand (SGh)

Horizontally laminated sands and silts (SFh, Sh) and sand with ripple-cross lamination (Src) point out shallow, low-energy, glaciofl uvial channels deposition in lower current regime. Climbing ripples suggest deposits agradation (Jopling & Walker, 1968). Horizontal lamination of SFh and FSh is probably related to the deposi-tion by low-energy sheet fl ows (Zielinski & van Loon 1999, 2000).

Horizontally laminated sand and gravel bed (SGh) represent fl ow with higher-energy in trans-itional condition between lower and upper fl ow regime. SGh as well as SFh and FSh can occur in sheet fl ows.

High-energy glaciofl uvial channel

GDp, GDm represent high-energy sub-envi-ronments. First lithofacies (GDp) is cross-strati-fi ed gravel, clast-supported, with coarse grained matrix. Second lithofacies is massive gravel with medium matrix – GDm. Both lithofacies sug-gest deposition in high-energy, deep glacifl uvial channel, where migrating bars occurred. In case of GDp, the transport was probably fast and short within progradation conditions.

Interpretation of sub-environments

Lithofacies mentioned above represent dif-ferent processes and sub-environments of de-position (Table 3). Although, at fi rst glance the surface sediments show high disorder, after detailed observation some regularities are no-ticeable. The coarse grained components

(boul-Fig. 4. Distribution of dominated surface sediments within the frontal moraine complex of Ragnar glacier (Zone D on Fig. 1B)

TABLE. 3. LITHOFACIESANDTHEIRINTERPRETATIONFORTHEFRONTALMORAINECOMPLEXOFTHE RAGNARGLACIER. LITHOFACIES SUB--ENVIRONMENT OF SEDIMENTS DEPOSITION INTERPRETATION Sandy lithofacies Src Shallow channels 1. current sedimentation 3. lower regime of fl ow 4. low-energy, shallow fl ow 5. traction

6. aggradation with high sediments delivery

SFh Shallow channels

1. current sedimentation 2. sheet fl ows

3. transitional conditions between lower and upper fl ow regime 4. low-energy, shallow fl ow

SGh Channels 1. sheet fl ow_{2. transitional conditions between lower and upper fl ow regime}

Silty Facies

Fm Ponds 1. decantation

FSh Channels and ponds

1. sheet fl ows 2. shallow fl ows 3. lower regime fl ow

4. low-energy fl ow deposition

Diamictons

Dm Ice-cored moraines 1. debris fl ows2. redepositional processes 3. water content < 25%

GDm Channels and depres-sions between ice-cored moraines

1. water content >25%

2. the role of excess water in deposition 3. redepositional processes

4. hyperconcentrated fl ow

SDm Ponds and depressions between ice-cored mo-raines

1. water content >25%

2. the role of excess water in deposition 3. redepositional processes

4. hyperconcentrated fl ow

GDp Glaciofl uvial channels 1. progradational deposition2. hyperconcentrated fl ow 3. low-energy fl ow deposition

ders and coarse gravels) are mainly present at the distal part of the frontal moraine complex, on external slopes of the outer moraine ridges. The ratio of fi ne-grained component to boulder and gravel fraction increases toward the progla-cial lake (i.e. to the inner part of frontal moraine complex) (Fig. 4).

The intensity and variability of depositional processes from early stage of the frontal moraine complex formation to present

Several processes (Table 3) are interpreted as responsible for sediments deposition within the frontal moraine complex of the Ragnar glacier: hyperconcentrated fl ow, glaciofl uvial channeli-zed fl ow, glaciolacustrine sedimentation and de-bris fl ows. Lawson (1979) estimated that 95% of deposits present at the Manatuska glacier mar-ginal zone were redeposited. The similar can be observed in case of the Raganr glacier. Debris fl ows dominated in the early stage of the fron-tal moraine complex development, but now the ice-cores are isolated by thick, up to 2 m, debris cover and only in few points of the frontal mora-ine complex the ice is exposed. The thick debris cover slowed down the downwasting and back-wasting processes.

The fl uvial processes probably were and still are mostly limited to the river banks and periodi-cal streams. However, the role of fl uvial sedimen-tation was higher in the early stage of the fron-tal moraine complex creation, probably due to more intense ice-cores melting, generating large amount of meltwater. Glaciolacustrine sedimen-tation was also more intense in the past, because presently the considered area is relatively dry. Therefore, only few water-fi lled ponds occur. It is also thought that the aeolian activity plays restric-ted role in sediments transformation with similar intensity from past till now. Occurrence of the glaciolacustrine deposits in topographic heights suggests that the intense sedimentation and re-sedimentation processes caused at least one topo-graphic inversion.

Generally, in case of frontal moraine complex of the Ragnar glacier, most of the sediments are resedimented within the marginal zone and do not transferred outside to proglacial system.

Conclusions

Presently the frontal ice-cored moraine com-plex is relatively stable and small quantity of de-bris undergo displacement. The intensive resedi-mentation is restricted to few areas: affected by river activity and some parts of steep ridges with directly exposed ice-cores, where the mass move-ment processes occur with high intensity. Except these areas the thick debris cover isolates the ice-cores from melting.

Resedimentation processes were the main factor infl uencing on the morphology and sedi-ments distribution in the early stage of the ice-cored moraine complex creation as well as now-adays. But the intensity of gravity fl ows is much lower now. The high vertical diversifi cation within lithofacies suggests the high ratio of sub-environmental transformation during the time. The glacolacustrine and glaciofl uvial processes are suggested to be less important now than in the early stage of the frontal moraine complex development. In case of aeolian activity, their role is relatively stable from the LIA till now, but the facies refl ecting the aeolian processes activity are hard to be identifi ed because of still higher role of mass movement, fl uvial and lacustrine processes.

Acknowledgements

The fi eldwork was fi nancially supported by the Polish National Committee on Scientifi c Re-search (KBN) (Grant No. 6 PO4E 041 21, Grant No. 2 P04G 040 28) and Polish Ministry of Science and Higher Education (Grant No. 3505/P01/2007/32). Members of the Adam Mickiewicz University expeditions to Svalbard in years 2005 and 2007 helped with the fi eldwork. To all these institutions and persons we extend our sincere thanks. M. Ewertowski was supported by Kulczyk Founda-tion fellowship.

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